Global deformation from the great 2004 Sumatra-Andaman Earthquake observed by GPS: Implications for rupture process and global reference frame
|
|
- Shona Rich
- 5 years ago
- Views:
Transcription
1 Earth Planets Space, 58, , 2006 Global deformation from the great 2004 Sumatra-Andaman Earthquake observed by GPS: Implications for rupture process and global reference frame Corné Kreemer, Geoffrey Blewitt, William C. Hammond, and Hans-Peter Plag Nevada Bureau of Mines and Geology, and Seismological Laboratory, University of Nevada, Reno, MS 178, NV , U.S.A. (Received June 30, 2005; Revised October 17, 2005; Accepted November 9, 2005; Online published February 17, 2006) Static coseismic offsets >1 mm are observed up to 7800 km away from the great Sumatra-Andaman earthquake of 26 Dec using global GPS network data. We investigate the rupture process based on far-field continuous GPS data. To reduce error in the coseismic offset estimates due to post-seismic deformation in the days following the main shock, we simultaneously fit a model of co- and postseismic offsets for nearby stations SAMP (500 km) and NTUS (900 km). The 3-month cumulative postseismic displacement for station SAMP amounts to 20% of the coseismic displacement, and can be well modeled by velocity-strengthening afterslip. We find that coseismic slip on the northern rupture segment is 3 m, which is consistent with seismic estimates. Our best estimate of the moment magnitude is M w = 9.13 if we take into account the expected increase of the shear modulus with depth (for uniform μ = 30 GPa, the moment-magnitude would only be 8.97). Our geodetic results, and thus our inferred rupture model, are different from a similar study using far-field data of Banerjee et al. (2005). These differences highlight the challenge in earthquake studies on a global scale in terms of the sensitivity of far-field offset estimates to the analysis strategy and reference frame treatment. Our predicted coseismic offsets from this event are at least 1 mm across almost the entire globe. This warrants a reconsideration of how to maintain the global terrestrial reference frame affected by earthquakes of M w > 9.0. Key words: GPS, Great Sumatra-Andaman Earthquake, earthquake rupture, coseismic displacements, postseismic deformation. 1. Introduction The great Sumatra-Andaman earthquake of 26 December, 2004 is the first earthquake to be observed by modern geodetic techniques across the globe. This event provides unprecedented opportunities to study such an earthquake on a global scale, to verify our geodetic and geophysical models, and to infer solid earth deformation processes on a large range of time and spatial scales. Much debate has occurred on the magnitude estimate of this earthquake using seismologic data. The original broad-band estimate from the Harvard CMT project was M w = 9.0. The initial analysis of the Earth s free oscillations yielded M w = 9.3 (Stein and Okal, 2005). Both estimates have since then been revised; long period analysis is now consistent with M w = 9.2 (Lay et al., 2005), and a revision of the free oscillation analysis is now consistent with M w = 9.15 (Park et al., 2005). The time that was needed for the different analyses to converge towards a consistent value leaves room for much improvement. Spacegeodesy can provide an independent, and potentially (near) real-time, magnitude estimate. Also, GPS can provide additional constraints on the rupture process. Current estimates from seismology can vary significantly depending on the choice of analysis (Ammon et al., 2005). Limited analysis of the time-series of SAMP and NTUS Copyright c The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. was presented by (Khan and Gudmundsson, 2005). A much more detailed study was presented by Vigny et al. (2005), who used a large amount of regional data (and some from far-field IGS stations) to put strong constraints on the extend and total slip along the rupture. Their analysis was, however, hindered by not taking into account possible postseismic offsets for continuous sites in the 14 days after the event, and by using an elastic half-space model instead of a spherical model approach. In this study we focus on the ability to put constraints on the rupture process using far-field GPS static offsets. We focus on far-field offsets, because an M w > 9.0 event will create offsets over a large part (or all) of the globe such that the offset estimates are particularly sensitive to analysis approach (e.g., common-mode analysis) and reference frame treatment. Many other future subduction zone earthquakes are located in regions where only far-field data will be available. Banerjee et al. (2005), hereafter referred to as BPB, analyzed the time-series of 41 mainly far-field stations. They showed millimeter static offsets at GPS stations thousands of kilometers away from the earthquake rupture. We also calculate far-field static offsets, but using a different processing technique and applying a different analysis approach. Straight-forward estimates of static offsets from time-series for stations near the rupture are problematic, because of possible rapid postseismic deformation. We offer an alternative treatment of the time-series for those stations; i.e. SAMP and NTUS. 141
2 142 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS Fig. 1. Time-series of east and north components of the daily positions for four representative stations (IISC, DGAR, KUNM, TNML). Days are relative to December 26, 2004 (day 0). Error-bars are formal 1-sigma uncertainties. Time-series have been detrended using the secular station velocity, and are shown here relative to the average position (dashed line) of the 28 days before December 26, The average position (dashed line) of the 28 days after the earthquake is indicated as well, and is reported for all stations in Table Data GPS data from 1 January 2000 to 27 March 2005 were processed from 27 stations within 7800 km of the rupture zone using the GIPSY OASIS II software package from the Jet Propulsion Laboratory (JPL). All stations are part of the network maintained by the International GPS Service (IGS), except SAMP, which is maintained by the BAKO- SURTANAL Indonesian network. Station coordinates were estimated every 24 hours using the precise point positioning method (Zumberge et al., 1997) with ambiguity resolution applied successfully across the entire network by automatic selection of the ionospheric- or pseudorangewidelane method (Blewitt, 1989). Satellite orbit and clock parameters, and daily coordinate transformation parameters into the global reference frame (ITRF2000) were provided by JPL. Ionosphere-free combinations of carrier phase and pseudorange were processed every 5 minutes. Estimated parameters included a tropospheric zenith bias and two gradient parameters estimated as random-walk processes, and station clocks estimated as a white-noise process. Station velocities were estimated using all available data from 1 January 2000 to 25 December 2004 (with most stations providing data for the entire period). These velocities were then used to detrend all the data (through 27 March 2005). To reduce the impact of coseismic displacements on the reference frame, all daily solutions were then transformed (by a 7-parameter Helmert transformation) onto the constant velocity solution using only stations >4000 km from the epicenter. Formal errors for daily station positions were computed assuming 10-mm 1-standard deviation errors in the ionosphere-free carrier phase data. These errors were then realistically scaled by a factor of 2.1 (to normalize the reduced χ 2 of the fit to the constant velocity model). 2.1 Time-series To estimate the static coseismic displacements we calculated the difference between the average position for 28 days before and 28 days after the earthquake. The daily solution for 26 December, 2004 was not used. For the two closest stations, SAMP and NTUS, we followed a different procedure (see Section 2.2). We show the daily east and north positions for this time interval for stations IISC, DGAR, KUNM, and TNML (Fig. 1). These are indicative time-series, and similar data were also shown by BPB from their analysis. 2.2 Postseismic afterslip The time-series of stations SAMP and NTUS indicate a non-linear trend after the earthquake (Fig. 2). Therefore, to properly estimate the coseismic displacements for these
3 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS 143 Fig. 2. Detrended time-series of the east and north components of the daily positions for stations NTUS and SAMP relative to the average position of the 20 days before December 26, 2004 (day 0). Shown are the results of a simultaneous solution for the best-fitting coseismic offsets (Table 1) and a logarithmic decay function (dashed lines) assuming that the postseismic displacements are due to afterslip. stations, we use a method different from that applied to the other far-field stations. GPS postseismic time-series after other (subduction-type) earthquakes have been analyzed elsewhere to evaluate different possible mechanisms that could explain the data (e.g., Melbourne et al., 2002). Studies have found that afterslip occurring down-dip from the rupture plane is the dominant mechanism for subduction zone thrust events in Kamchatka and the Japan Trench (e.g., Heki et al., 1997; Bürgmann et al., 2001). For the December 26, 2005, event Vigny et al. (2005) noted that the apparent logarithmic decay in the time-series of regional GPS sites suggested that the postseismic deformation may indicate an afterslip process. For SAMP and NTUS we have used the times-series from 20 days before 26 December, 2004 until 27 March, 2005 (i.e., the day before the M w = 8.7, Northern Sumatra event) to simultaneously solve for the horizontal coseismic offsets and a logarithmic function describing the afterslip process after the event (Fig. 2). The 20 days prior to the event are used to constrain an average pre-seismic position. The inferred coseismic offsets are reported in Table 1. For the postseismic time-series we fit the following function for each station: ū =ā ln(bt + 1) (Marone et al., 1991). Here, b is the decay constant, and we solve for a single b value using the four time-series (east and north) of both stations. We find that b = 0.11 day 1, or 40.2 yr 1, which implies that 65% of the postseismic displacements expected within the first year has occurred within the 91 days that we analyzed after the earthquake. For our best-fit model we find a(x) = 11 mm and a(y) = 3mm for SAMP, and a(x) = 1mm and a(y) = 1 mm for NTUS. Table 1. GPS-derived coseismic offsets. Site Lon. Lat. D east north σ east σ north ( E) ( N) (km) (mm) (mm) (mm) (mm) ALIC BAHR BAKO COCO DARW DGAR GUAM HRAO HYDE IISC KARR KIT KUNM LAE LHAS MALI MBAR MALD NTUS PIMO REUN SAMP SEY TNML TOW TSKB WUHN D, distance from site to epicenter. 1 our coseismic offsets for SAMP and NTUS are determined simultaneously with parameters for a postseismic afterslip process (see Fig. 2). The uncertainties for these sites were determined similarly to those of other sites. The 3-month cumulative postseismic displacements represent 20% and 14% of the initial coseismic displacements for SAMP and NTUS, respectively. 2.3 Coseismic displacements The inferred coseismic displacements are listed in Table 1 and shown in Fig. 3. Generally, displacements are towards the epicenter, with amplitude decaying with distance. The magnitude of the far-field displacements northeast and southwest of the rupture are greater than to the northwest and southeast, consistent with a thrust mechanisms along a northwest-southeast trending fault. For example the site TNML moves nearly twice the distance of KARR which has a similar epicentral distance. Our results and those of BPB exhibit a similar general pattern. Although differences at any individual site may not be significant, some important systematic differences exist (Fig. 3). Our estimate for NTUS is more than 1.5 larger than that of BPB. For stations IISC, HYDE, and TNML, predicted directions between both studies are very close, but BPB offsets are % larger. A similar discrepancy in rate also exists for PIMO, WUHN, DGAR, (and to lesser extent KUNM), however BPB estimates are all directed considerably more southward than our predicted directions. Also for stations LAE1, BAKO, and COCO are the BPB estimates directed more southward. For African
4 144 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS Fig. 3. Observed coseismic displacements from this study and Banerjee et al. (2005). Uncertainties are shown as 68% confidence ellipses. Rupture segments used in this study and by Banerjee et al. (2005) are shown in dark gray (there are shallow and deep segments). The dashed displacements for station SAMP are plotted at half the scale as the other vectors. stations (for which BPB did not present estimates) we find consistent eastward offsets of mm. 3. Rupture Model The far-field coseismic displacements are sensitive to the distribution of coseismic slip along the Indian-Burma plate boundary during the earthquake. For simplicity and comparison, we model the rupture as slip on planes identical to those found by BPB. The location and dip of the rupture planes is rather well supported by the seismicity (Engdahl et al., 1998; Lay et al., 2005). The difference between our far-field offsets and those of BPB requires changes in the rake and slip parameters inferred by BPB (their model M3). Like BPB, we use a layered spherical Earth model (Pollitz, 1996) and the PREM elastic stratification (Dziewonski and Anderson, 1981) to calculate static offsets. We use spherical harmonic degrees from l = 1 to l = In the M3 model of BPB the fault rupture is divided into 3 segments. The northern segment has uniform slip up to 30 km depth only, with the segment divided along strike into four sub-segments, each with their own estimated rake. The central and southern segment each has one rake estimate, and has a deep (i.e., km) as well as shallow segment, each with similar slip offsets. In our first model (A), we estimate the misfit between our observations and the predicted static offsets when we use the rake and slip estimates of BPB. We present our misfit in terms of χν 2, which is the reduced χ 2 (i.e., χ 2 divided over N n, with N the number of data constraints, and n the number of free model parameters) (Table 2). We will see next that the data fit for model A is relatively poor. Our coseismic observations imply therefore a considerably different rupture model than the one of BPB. In our second model (B) we keep the rake estimates of BPB and solve for the slip offsets for the three segments such that the χν 2 is minimized. Fault parameters are shown in Table 2. χν 2 estimates are relatively insensitive to small variations in slip, therefore we find a range of model parameters that would result in roughly the same χν 2. We use this range to assign uncertainties in our model parameters (Table 2). In model C we solve simultaneously for slip offsets for the three segments, as well as for rake estimates for the four sub-segments of segment 1, and for segment 2. Like BPB, we set the rake for segment 3 to 90. For this model we find left-lateral oblique slip for Segment 1. This result is
5 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS 145 Table 2. Rupture model parameters and goodness of fit. Model λ 1 a, λ 1 b, λ 1 c, λ 1 d, λ 2, λ 3, U 1,m U 2,m U 3,m χν 2 A B ± ± ± C 50±10 50±10 50±10 50±10 104± ± ± ± D ± ± ± ± λ, rake; U, slip. Subscripts 1 3 indicate north to south segments of Banerjee et al. (2005), and a-d are north to south sub-segments of segment 1. χν 2 is the reduced χ 2 Model parameters in italics are fixed, values in bold are solved for in this study. Model A is similar to model M3 of Banerjee et al. (2005). See text for descriptions of models B D. Fig. 4. Observed coseismic displacements from this study and predicted displacements from model C. Uncertainties in observed vectors are shown as 68% confidence ellipses. Rupture segments are shown in dark gray. The dashed displacements for station SAMP are plotted at half the scale as the other vectors. not compatible with the seismotectonic context and is also inconsistent with slip vectors of aftershocks along the Andaman segment inferred from the Harvard CMT solutions. Therefore, in our final model D, we constrain the rake of the sub-segments of Segment 1 to pure dip-slip. We find that the χν 2 for model C is larger than for model D, thus solving for the rakes on Segment 1 does not improve the fit. To evaluate whether our fit for model D is a significant improvement over the fit for model B, we perform an F-test and find the improvement to be significant. Thus although our data cannot distinguish between models with dip-slip or left-lateral oblique slip on Segment 1, our data precludes right-lateral oblique slip, as found by BPB. Our predicted offsets for model D are shown in Fig. 4 together with our coseismic offsets. 4. Discussion 4.1 Revised rupture interpretation There are two main differences between the rupture models we inferred here from our coseismic observations and the models of BPB. First, we find only 3 m offset on Segment 1, which is much lower than the 10.5±0.5 for BPB s preferred model M3. This is a direct result of the fact that our coseismic offsets in India and Southeast Asia
6 146 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS are much lower than their estimates. Our result is much more consistent with the <2 m obtained for the Andaman (i.e., northern) segment from seismic modeling (Ammon et al., 2005; Lay et al., 2005). Secondly, our data does not require oblique slip on the Andaman segment (however, it does for the Nicobar (middle) segment), as found by BPB. All geodetic models on the earthquake rupture from both our study and BPB are in two major ways in disagreement with seismic models of the earthquake rupture (Ammon et al., 2005; Ishii et al., 2005; Krüger and Orhnberger, 2005) and other observations (Bilham et al., 2005). First, the seismic models suggest that the maximum peak in seismic energy or displacement is near northern Sumatra, and not near the Nicobar Islands where the segment with the highest slip (Segment 2) of the geodetic models is located. The geodetic results are more in agreement with the analysis of normal modes excited by the event. Those studies place the centroid at 7.5 north latitude (Park et al., 2005; Stein and Okal, 2005), close to where the far-field coseismic offsets constrain the maximum slip to be, and significantly north of the CMT epicenter. Secondly, Bilham et al. (2005) inferred from vertical offset observations respectively m and 5 10 m for slip along parts of the Nicobar and Andaman segments of the rupture, consistently more than our and BPB estimates for the Nicobar segment and our result for the Andaman segment. However, the large observed offsets are concentrated along only very small portions of the rupture (e.g., Simeulue Island) and such details are not resolvable using far-field offsets alone, but has been seen/modeled with regional GPS data (Vigny et al., 2005). For the southern segment geodetically derived estimates of 6 m are not inconsistent with the average7mfound from seismic modeling (Lay et al., 2005). Clearly, to understand better, or resolve, the difference between the seismic and geodetic results, regional geodetic data is important (Vigny et al., 2005). Some of the discrepancies noted above are expressed in the inferred moment magnitude between the different geodetic and geologic models. When using a shear modulus of μ = 30 GPa, which is generally used for continental earthquakes, model C corresponds to an M 0 = N m, equivalent to M w = This value is much lower than that of BPB or published seismic estimates derived from long-period broadband data (Lay et al., 2005) or free oscillations (Park et al., 2005; Stein and Okal, 2005). The only way to reconcile our moment estimate with the seismic estimates is to assume larger values for the shear modulus than 30 GPa. It has been shown (Bilek and Lay, 1999) that the shear modulus can increase significantly with depth along a subduction interface, with values lower than 30 GPa in unconsolidated sediments at very shallow depths, and values over 100 GPa at km depth. The PREM model also implies a depth increase of the shear modulus with depth. When we chose a permissible shear modulus of 40 GPa as average for the 0 30 depth segments, and 100 GPa as average for the km depth segments (Bilek and Lay, 1999), we obtain M w = 9.13 (M 0 = N m), which is very close to the M w = 9.15 from the latest analysis of free oscillations (Park et al., 2005). Thus, if our coseismic offsets, our rupture analysis, and the result by Park et al. (2005) are all reasonable, then our results indicate a significant increase of the shear modulus with depth, as expected. Improved knowledge of the shear modulus and its variation with depth (as well as other parameters that may vary between subduction zones) is therefore an important asset in magnitude determination using GPS. In any case, geodesy can provide important (near) real-time constraints on the earthquake size and thereby alleviate the difficulties to derive the magnitude quickly from seismology. 4.2 Afterslip implications Our analysis of the postseismic time-series for NTUS and SAMP indicate that postseismic displacements are not subparallel to coseismic displacements. More specifically, for stations SAMP and NTUS the direction of postseismic offset is 10 more southward and 20 more northward, respectively, compared to the coseismic direction. That is, for SAMP postseismic displacements are directed more normal to southern rupture plane, and for NTUS more parallel to southern rupture plane, compared to coseismic offsets. Further north, near Phuket, Thailand, Vigny et al. (2005) found the post- and coseismic offsets to be parallel. Although our results are important to infer the actual afterslip process, particularly where it is occurring with respect to the rupture, we can not infer any more details on the afterslip process. Because of our emphasis on far-field GPS sites, and because postseismic processes are still ongoing as of this writing, we have not analyzed all the near-field geodetic data needed to definitively constrain postseismic afterslip in the vicinity of the rupture plane. However, our results suggest that after 1 year the postseismic displacement at SAMP and NTUS will be 30% and 23% of the coseismic displacement, respectively. This is relatively small compared to some cases observed elsewhere (e.g., Heki et al., 1997; Márquez Azúa et al., 2002), and is also small compared to our preliminary analysis of postseismic time-series after the M w = 8.7 March 28, 2005, event for which afterslip seems rapid and extensive (at SAMP 80% of coseismic offset is predicted to be accumulated as postseismic displacement 1 year after that event). The difference in postseismic offsets, and related afterslip processes, for the two Sumatra earthquakes may be explained, among several reasons, by the consideration that the rupture of the first event broke the surface, and the second did not. This would be consistent with the fact that the first event generated a large tsunami, and the second event did not. Moreover, it could explain the rapid afterslip we observe after the second event in terms of afterslip within the sediments up dip from the rupture. 4.3 Implications on global geodetic reference frame We have shown that observed coseismic offsets are generally well above 1 mm at 7000 km from the earthquake rupture. We find from our model C that expected displacements are in fact >1 mm for almost anywhere across the Earth s surface (Fig. 5). This has profound implications for the realization of the terrestrial reference frame, as station coordinates are currently being measured with 1 mm-level precision. This reference frame problem only arises now because this is the first earthquake in history that has deformed the entire Earth s surface at a detectable level. The last earthquake of M w > 9.0 occurred 40 years ago (in Alaska), well before modern space geodesy even existed.
7 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS 147 Fig. 5. Contours (in millimeters) of predicted total horizontal displacements from our coseismic model C. The expected displacements are >1 mm almost everywhere on the Earth s surface. One immediate problem is to define the meaning of a coseismic offset when the entire Earth surface has moved coseismically. Prior to the 2004 Sumatra earthquake, the definition was simply in terms of how far a station had moved with respect to stations in the far field, where it was possible to find a station sufficiently far from the earthquake that its displacement was completely negligible. This is no longer the case. In our analysis, we have defined the reference frame in terms of the average position of stations more than 4000 km from the rupture, but this is clearly an ad hoc solution until clearer conventions are debated and agreed upon. One rigorous solution we propose would be to use a model of the surface displacement in a reference frame that has no-net translation with respect to the modeled center of mass of the entire Earth (including the static ocean response), and no-net rotation with respect to the modeled Earth surface. Observed coseismic displacements could then be defined within a frame where there is no-net translation or rotation of the residual station coordinates (observed minus the modeled displacements). One challenge with this approach is that various models might explain the observed deformation to within the errors. Another challenge is that typically such models are adjusted to fit the data, and that care must be taken to ensure that this is done in a way that is self-consistent with the reference frame definition. A third challenge is that, as we have shown for some stations, coseismic offsets might represent only a fraction of the total station motion caused by the earthquake. And finally, for some far-field stations coseismic offsets may be of the same order of magnitude, or smaller, than the effects of possible station instability or incorrectly modeled tropospheric delay (see, for instance, the anomalous offset at SEY1). A related problem is how to define the coordinates of the entire global geodetic network now that such a great earthquake has taken place. Clearly this relates to the above problem, in that offsets could be estimated within a modelspecific frame, and added to the pre-seismic coordinates. However, note that this requires that a conventional earthquake displacement model be selected (and clearly specified) in order to maintain a conventional international terrestrial reference frame. In principle, such a model should be specified for all great earthquakes. The process toward developing and agreeing upon a conventional model for every great earthquake would certainly be a challenge for the geodetic community. 5. Conclusions We have estimated and analyzed coseismic static offsets of far-field GPS stations from the 26 December, 2004, earthquake. In this process we also found and analyzed significant postseismic displacements for nearby stations (specifically SAMP), which are consistent with a velocitystrengthening afterslip process. At many locations, our coseismic offsets are systematically different than those obtained by BPB. These differences are the result of using different analysis strategies and underscore the need for a conventional geodetic approach when dealing with displacements from an earthquake with M w > 9.0. The main difference between our rupture model and that of BPB is that we find a much lower slip on the northern rupture segment, which is more consistent with seismic studies. Consequently we find a much lower M w than BPB and, more importantly, than independent earthquake studies using free oscillations. The only way to resolve this difference is to use a significant increase in shear modulus with depth when estimating our seismic moment. We argue that an M w = 9.13 from our result is permissible. Our predicted coseismic offsets from this event are at least 1 mm across almost the entire globe. This warrants a reconsideration of how to maintain the global terrestrial reference frame affected by earthquakes of M w > 9.0.
8 148 C. KREEMER et al.: 2004 SUMATRA-ANDAMAN EARTHQUAKE DEFORMATION OBSERVED BY GPS Acknowledgments. We thank F. Pollitz for his help and for making his spherical coseismic programs available, and two anonymous reviewers for comments on the manuscript. We are grateful to the International GPS Service and BAKOSURTANAL for making GPS data freely available and to the Jet Propulsion Laboratory for the GIPSY OASIS II software and precise GPS orbit products. References Ammon, C. J., C. Ji, H.-K. Thio, D. Robinson, S. Ni, V. Hjorleifsdottir, H. Kanamori, T. Lay, S. Das, D. Helmberger, G. Ichinose, J. Polet, and D. Wald, Rupture process of the 2004 Sumatra-Andaman earthquake, Science, 308, , Banerjee, P., F. F. Pollitz, and R. Bürgmann, The size and duration of the Sumatra-Andaman earthquake from far-field static offsets, Science, 308, , Bilek, S. L. and T. Lay, Rigidity variations with depth along interplate megathrust faults in subduction zones, Nature, 400, , Bilham, R., R. Engdahl, N. Feldl, and S. P. Satyabala, Partial and complete rupture of the Indo-Andaman plate boundary , Seismological Research Letters, 76, , Blewitt, G., Carrier phase ambiguity resolution for the Global Positioning System applied to geodetic baselines up to 2000 km, Journal of Geophysical Research, 94, 10,187 10,283, Bürgmann, R., M. G. Kogan, V. E. Levin, C. H. Scholz, R. W. King, and G. M. Steblov, Rapid aseismic moment release following the 5 December, 1997 Kronotsky, Kamchatka, earthquake, Geophysical Research Letters, 28, , Dziewonski, A. M. and D. L. Anderson, Preliminary reference Earth model, Physics of the Earth and Planetary Interiors, 25, , Engdahl, E. R., R. van der Hilst, and R. Buland, Global teleseismic relocation with improved travel times and procedures for depth determination, Bulletin of the Seismological Society of America, 88, , Heki, K., S. Miyazaki, and H. Tsuji, Silent fault slip following an interplate thrust earthquake at the Japan Trench, Nature, 386, , Ishii, M., P. M. Shearer, H. Houston, and J. E. Vidale, Extent, duration and speed of the 2004 Sumatra-Andaman earthquake imagined by the Hi-Net array, Nature, 435, , Khan, S. A. and O. Gudmundsson, GPS analysis of the Sumatra-Andaman earthquake, EOS Transactions, 86, 89 94, Krüger, F. and M. Orhnberger, Tracking the rupture of the M w = 9.3 Sumatra earthquake over 1,150 km at teleseismic distance, Nature, 435, , Lay, T., H. Kanamori, C. J. Ammon, M. Nettles, S. N. Ward, R. C. Aster, S. L. Beck, M. R. Brudzinski, R. Butler, H. R. DeShon, G. Ekström, K. Satake, and S. Sipkin, The Great Sumatra-Andaman earthquake of 26 December 2004, Science, 308, , Marone, C. J., C. H. Scholz, and R. Bilham, On the mechanics of earthquake afterslip, Journal of Geophysical Research, 96, , Márquez Azúa, B., C. DeMets, and M. Masterlark, Strong interseismic coupling, fault afterslip, and viscoelastic flow before and after the Oct. 9, 1995 Colima-Jalisco earthquake: Continuous GPS measurements from Colima, Mexico, Geophysical Research Letters, 29, 1281, doi: /2002gl014702, Melbourne, T. I., F. H. Webb, J. M. Stock, and C. Reigber, Rapid postseismic transients in subduction zones from continuous GPS, Journal of Geophysical Research, 107, 2241, doi: /2001jb000555, Park, J., T. A. Song, J. Tromp, E. Okal, S. Stein, G. Roult, E. Clevede, G. Laske, H. Kanamori, P. Davis, J. Berger, C. Braitenberg, M. van Camp, X. Lei, H. Sun, H. Xu, and S. Rosat, Earth s free oscillations excited by the 26 December 2004 Sumatra-Andaman earthquake, Nature, 308, , Pollitz, F. F., Coseismic deformation from earthquake faulting on a layered spherical Earth, Geophysical Journal International, 125, 1 14, Stein, S. and E. Okal, Speed and size of the Sumatra earthquake, Nature, 434, , Vigny, C., W. J. F. Simons, S. Abu, R. Bamphenyu, C. Satirapod, N. Choosakul, C. Subarya, A. Socquet, K. Omar, H. Z. Abidin, and B. A. C. Ambrosius, Insight into the 2004 Sumatra-Andaman earthquake from GPS measurements in southeast Asia, Nature, 436, , Zumberge, J. F., M. B. Heflin, D. C. Jefferson, and M. M. Watkins, Precise point positioning for the efficient and robust analysis of GPS data from large networks, Journal of Geophysical Research, 102, , C. Kreemer ( kreemer@unr.edu), G. Blewitt, W. C. Hammond, and H.-P. Plag
Solid Earth Deformations Induced by the Sumatra Earthquakes of : GPS Detection of Co-Seismic Displacements
Solid Earth Deformations Induced by the Sumatra Earthquakes of 2-25: GPS Detection of Co-Seismic Displacements and Tsunami-Induced Loading H.-P. Plag, G. Blewitt, C. Kreemer, W.C. Haond Nevada Bureau of
More informationSolid Earth Deformations Induced by the Sumatra Earthquakes of : GPS Detection of Co-Seismic Displacements
Solid Earth Deformations Induced by the Sumatra Earthquakes of 2-25: GPS Detection of Co-Seismic Displacements and Tsunami-Induced Loading H.-P. Plag, G. Blewitt, C. Kreemer, W.C. Haond Nevada Bureau of
More informationRapid Determination of Earthquake Magnitude using GPS for Tsunami Warning Systems: An Opportunity for IGS to Make a Difference
Rapid Determination of Earthquake Magnitude using GPS for Tsunami Warning Systems: An Opportunity for IGS to Make a Difference Geoffrey Blewitt, 1 Corné Kreemer, 1 William C. Hammond, 1 Hans-Peter Plag,
More informationThe Size and Duration of the Sumatra-Andaman Earthquake from Far-Field Static Offsets
The Size and Duration of the Sumatra-Andaman Earthquake from Far-Field Static Offsets P. Banerjee, 1 F. F. Pollitz, 2 R. Bürgmann 3 * 1 Wadia Institute of Himalayan Geology, Dehra Dun, 248001, India. 2
More informationSeismological Aspects of the December 2004 Great Sumatra-Andaman Earthquake
Seismological Aspects of the December 2004 Great Sumatra-Andaman Earthquake Hiroo Kanamori, a M.EERI The 2004 Great Sumatra-Andaman earthquake had an average source duration of about 500 sec. and a rupture
More informationRapid determination of earthquake magnitude using GPS for tsunami warning systems
Rapid determination of earthquake magnitude using GPS for tsunami warning systems Geoffrey Blewitt, 1 Corné Kreemer, 1 William C. Hammond, 1 Hans-Peter Plag, 1 Seth Stein, and Emile Okal The 6 December
More informationLarge surface wave of the 2004 Sumatra-Andaman earthquake captured by the very long baseline kinematic analysis of 1-Hz GPS data
Earth Planets Space, 58, 153 157, 2006 Large surface wave of the 2004 Sumatra-Andaman earthquake captured by the very long baseline kinematic analysis of 1-Hz GPS data Yusaku Ohta, Irwan Meilano, Takeshi
More information1.3 Short Review: Preliminary results and observations of the December 2004 Great Sumatra Earthquake Kenji Hirata
1.3 Short Review: Preliminary results and observations of the December 2004 Great Sumatra Earthquake Kenji Hirata We give a brief review about observations and preliminary results regarding the 2004 great
More informationA search for seismic radiation from late slip for the December 26, 2004 Sumatra-Andaman (M w = 9.15) earthquake
Click Here for Full Article GEOPHYSICAL RESEARCH LETTERS, VOL. 33, L18305, doi:10.1029/2006gl027286, 2006 A search for seismic radiation from late slip for the December 26, 2004 Sumatra-Andaman (M w =
More informationCoseismic Slip Distributions of the 26 December 2004 Sumatra Andaman and 28 March 2005 Nias Earthquakes from GPS Static Offsets
Bulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S86 S102, January 2007, doi: 10.1785/0120050609 E Coseismic Slip Distributions of the 26 December 2004 Sumatra Andaman and 28 March
More informationTrade-off between seismic source detail and crustal heterogeneities in spherical 3D finite element modeling: a 2004 Sumatra earthquake case study
ANNALS OF GEOPHYSICS, 54, 1, 2011; doi: 10.4401/ag-4639 Trade-off between seismic source detail and crustal heterogeneities in spherical 3D finite element modeling: a 2004 Sumatra earthquake case study
More informationElectronic supplement for Forearc motion and deformation between El Salvador and Nicaragua: GPS, seismic, structural, and paleomagnetic observations
DR2011053 Electronic supplement for Forearc motion and deformation between El Salvador and Nicaragua: GPS, seismic, structural, and paleomagnetic observations by D. Alvarado et al., Lithosphere, April,
More informationThe March 11, 2011, Tohoku-oki earthquake (Japan): surface displacement and source modelling
The March 11, 2011, Tohoku-oki earthquake (Japan): surface displacement and source modelling Salvatore Stramondo Bignami C., Borgstrom S., Chini M., Guglielmino F., Melini D., Puglisi G., Siniscalchi V.,
More informationInsight into the 2004 Sumatra Andaman earthquake from GPS measurements in southeast Asia
Vol 436 14 July 2005 doi:10.1038/nature03937 ARTICLES Insight into the 2004 Sumatra Andaman earthquake from GPS measurements in southeast Asia C. Vigny 1, W. J. F. Simons 2, S. Abu 3, Ronnachai Bamphenyu
More informationTitle. Author(s)Heki, Kosuke. CitationScience, 332(6036): Issue Date Doc URL. Type. File Information. A Tale of Two Earthquakes
Title A Tale of Two Earthquakes Author(s)Heki, Kosuke CitationScience, 332(6036): 1390-1391 Issue Date 2011-06-17 Doc URL http://hdl.handle.net/2115/48524 Type article (author version) File Information
More informationCrustal deformations associated with the great Sumatra-Andaman earthquake deduced from continuous GPS observation
Earth Planets Space, 58, 127 139, 6 Crustal deformations associated with the great Sumatra-Andaman earthquake deduced from continuous GPS observation Manabu Hashimoto 1, Nithiwatthn Choosakul 2, Michio
More informationSeparating Tectonic, Magmatic, Hydrological, and Landslide Signals in GPS Measurements near Lake Tahoe, Nevada-California
Separating Tectonic, Magmatic, Hydrological, and Landslide Signals in GPS Measurements near Lake Tahoe, Nevada-California Geoffrey Blewitt, Corné Kreemer, William C. Hammond, & Hans-Peter Plag NV Geodetic
More informationSource of the July 2006 West Java tsunami estimated from tide gauge records
GEOPHYSICAL RESEARCH LETTERS, VOL. 33, L24317, doi:10.1029/2006gl028049, 2006 Source of the July 2006 West Java tsunami estimated from tide gauge records Yushiro Fujii 1 and Kenji Satake 2 Received 13
More informationForecasting the effects of the Andaman Islands - Sumatra megathrust earthquakes (Dec and Mar. 2005) on volcanoes in the surrounding area.
Forecasting the effects of the Andaman Islands - Sumatra megathrust earthquakes (Dec. 2004 and Mar. 2005) on volcanoes in the surrounding area. Emanuele Casarotti a,, Jacopo Selva b a California Institute
More informationLow-Latency Earthquake Displacement Fields for Tsunami Early Warning and Rapid Response Support
Low-Latency Earthquake Displacement Fields for Tsunami Early Warning and Rapid Response Support Hans-Peter Plag, Geoffrey Blewitt Nevada Bureau of Mines and Geology and Seismological Laboratory University
More informationCoseismic Slip and Afterslip of the Great M w 9.15 Sumatra Andaman Earthquake of 2004
Bulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S15 S173, January 007, doi: 10.1785/010050631 Coseismic Slip and Afterslip of the Great M w 9.15 Sumatra Andaman Earthquake of 004
More informationBanda Aceh December 26th Earthquake monitored by GPS
Banda Aceh December 26th Earthquake monitored by GPS C. Vigny (1), W.J.F. Simons (2), S. Abu (3), Chalermchon Satirapod (4), M. Hashizume (5), Sarayut Yousamran (6), C. Subarya (7), K. Omar (8), H.Z. Abidin
More informationSeth Stein and Emile Okal, Department of Geological Sciences, Northwestern University, Evanston IL USA. Revised 2/5/05
Sumatra earthquake moment from normal modes 2/6/05 1 Ultra-long period seismic moment of the great December 26, 2004 Sumatra earthquake and implications for the slip process Seth Stein and Emile Okal,
More informationCoseismic slip distribution of the 1946 Nankai earthquake and aseismic slips caused by the earthquake
Earth Planets Space, 53, 235 241, 2001 Coseismic slip distribution of the 1946 Nankai earthquake and aseismic slips caused by the earthquake Yuichiro Tanioka 1 and Kenji Satake 2 1 Meteorological Research
More informationSegmentation in episodic tremor and slip all along Cascadia
Segmentation in episodic tremor and slip all along Cascadia Michael R. Brudzinski and Richard M. Allen Geology 35 (10) 907-910, 2007, doi: 10.1130/G23740A.1 Data Repository: Methods for Automated Data
More informationSpatially linked asperities of the great Kuril earthquakes revealed by GPS
GEOPHYSICAL RESEARCH LETTERS, VOL. 35, L22306, doi:10.1029/2008gl035572, 2008 Spatially linked asperities of the 2006 2007 great Kuril earthquakes revealed by GPS Grigory M. Steblov, 1,2 Mikhail G. Kogan,
More informationEmpirical Green s Function Analysis of the Wells, Nevada, Earthquake Source
Nevada Bureau of Mines and Geology Special Publication 36 Empirical Green s Function Analysis of the Wells, Nevada, Earthquake Source by Mendoza, C. 1 and Hartzell S. 2 1 Centro de Geociencias, Universidad
More informationGeodesy (InSAR, GPS, Gravity) and Big Earthquakes
Geodesy (InSAR, GPS, Gravity) and Big Earthquakes Mathew Pritchard Teh-Ru A. Song Yuri Fialko Luis Rivera Mark Simons UJNR Earthquake Research Panel, Morioka, Japan - Nov 6, 2002 Goals Accurate and high
More informationSLIP DISTRIBUTION FOR THE 2004 SUMATRA-ANDAMAN EARTHQUAKE CONSTRAINED BY BOTH GPS DATA AND TSUNAMI RUN-UP MEASUREMENTS
McKenzie D. and J. Jackson; 2002: Conditions for flow in the continental crust, Tectonics, 21, doi:10.1029/2002tc001394. McKenzie D. P.; 1977: The initiation of trenches: a finite amplitude instability,
More informationRupture Characteristics of Major and Great (M w 7.0) Megathrust Earthquakes from : 1. Source Parameter Scaling Relationships
Journal of Geophysical Research Solid Earth Supporting Information for Rupture Characteristics of Major and Great (M w 7.0) Megathrust Earthquakes from 1990-2015: 1. Source Parameter Scaling Relationships
More informationConstraints on 2004 Sumatra Andaman earthquake rupture from GPS measurements in Andaman Nicobar Islands
Earth and Planetary Science Letters 242 (2006) 365 374 www.elsevier.com/locate/epsl Constraints on 2004 Sumatra Andaman earthquake rupture from GPS measurements in Andaman Nicobar Islands V.K. Gahalaut
More informationCentroid moment-tensor analysis of the 2011 Tohoku earthquake. and its larger foreshocks and aftershocks
Earth Planets Space, 99, 1 8, 2011 Centroid moment-tensor analysis of the 2011 Tohoku earthquake and its larger foreshocks and aftershocks Meredith Nettles, Göran Ekström, and Howard C. Koss Lamont-Doherty
More informationSeismic and aseismic fault slip before and during the 2011 off the Pacific coast of Tohoku Earthquake
LETTER Earth Planets Space, 63, 637 642, 2011 Seismic and aseismic fault slip before and during the 2011 off the Pacific coast of Tohoku Earthquake Shin ichi Miyazaki 1, Jeffery J. McGuire 2, and Paul
More informationThe 2004 Indian Ocean tsunami: Tsunami source model from satellite altimetry
Earth Planets Space,, 9, The Indian Ocean tsunami: Tsunami source model from satellite altimetry Kenji Hirata, Kenji Satake, Yuichiro Tanioka 3, Tsurane Kuragano, Yohei Hasegawa, Yutaka Hayashi, and Nobuo
More informationGPS Strain & Earthquakes Unit 5: 2014 South Napa earthquake GPS strain analysis student exercise
GPS Strain & Earthquakes Unit 5: 2014 South Napa earthquake GPS strain analysis student exercise Strain Analysis Introduction Name: The earthquake cycle can be viewed as a process of slow strain accumulation
More informationNews Release December 30, 2004 The Science behind the Aceh Earthquake
News Release December 30, 2004 The Science behind the Aceh Earthquake PASADENA, Calif. - Kerry Sieh, the Robert P. Sharp Professor of Geology at the California Institute of Technology and a member of Caltech's
More informationDETERMINATION OF SLIP DISTRIBUTION OF THE 28 MARCH 2005 NIAS EARTHQUAKE USING JOINT INVERSION OF TSUNAMI WAVEFORM AND GPS DATA
Synopses of Master Papers Bulletin of IISEE, 47, 115-10, 013 DETERMINATION OF SLIP DISTRIBUTION OF THE 8 MARCH 005 NIAS EARTHQUAKE USING JOINT INVERSION OF TSUNAMI WAVEFORM AND GPS DATA Tatok Yatimantoro
More informationDeformation cycles of great subduction earthquakes in a viscoelastic Earth
Deformation cycles of great subduction earthquakes in a viscoelastic Earth Kelin Wang Pacific Geoscience Centre, Geological Survey of Canada School of Earth and Ocean Science, University of Victoria????
More informationRupture Process of the Great 2004 Sumatra-Andaman Earthquake
Rupture Process of the Great 2004 Sumatra-Andaman Earthquake Supporting Online Materials Submitted to Science, March 12, 2005 Charles J. Ammon 1, Ji Chen 2, Hong-Kie Thio 3, David Robinson 5, Sidao Ni
More informationChange of Strain Rate in Thailand after the 26 December 2004 and 28 March 2005 Earthquakes Using GPS Measurements
KSCE Journal of Civil Engineering (010) 14():15-0 DOI 10.1007/s105-010-015-4 Surveying and Geo-Spatial Information Engineering www.springer.com/105 Change of Strain Rate in Thailand after the 6 December
More informationReport on Banda Aceh mega-thrust earthquake, December 26, 2004
Report on Banda Aceh mega-thrust earthquake, December 26, 2004 Prepared January 7 th 2005 by C. Vigny, on behalf of the SEAMERGES (*) participants On the morning of December 26 th in SE Asia, 30 km below
More informationScaling relations of seismic moment, rupture area, average slip, and asperity size for M~9 subduction-zone earthquakes
GEOPHYSICAL RESEARCH LETTERS, VOL. 4, 7 74, doi:1.12/grl.976, 213 Scaling relations of seismic moment, rupture area, average slip, and asperity size for M~9 subduction-zone earthquakes Satoko Murotani,
More informationCoulomb stress change for the normal-fault aftershocks triggered near the Japan Trench by the 2011 M w 9.0 Tohoku-Oki earthquake
Earth Planets Space, 64, 1239 1243, 2012 Coulomb stress change for the normal-fault aftershocks triggered near the Japan Trench by the 2011 M w 9.0 Tohoku-Oki earthquake Tamao Sato 1, Shinya Hiratsuka
More information14 S. 11/12/96 Mw S. 6/23/01 Mw S 20 S 22 S. Peru. 7/30/95 Mw S. Chile. Argentina. 26 S 10 cm 76 W 74 W 72 W 70 W 68 W
175 Chapter 5 Comparision of co-seismic and post-seismic slip from the November 12, 1996, M w 7.7 and the June 23, 2001, M w 8.4 southern Peru subduction zone earthquakes 176 Abstract We use InSAR and
More informationCrustal deformation by the Southeast-off Kii Peninsula Earthquake
Crustal deformation by the Southeast-off Kii Peninsula Earthquake 51 Crustal deformation by the Southeast-off Kii Peninsula Earthquake Tetsuro IMAKIIRE, Shinzaburo OZAWA, Hiroshi YARAI, Takuya NISHIMURA
More informationIntroduction to the Special Issue on the 2004 Sumatra Andaman Earthquake and the Indian Ocean Tsunami
Name /mea_ssa971a_605412/971_05633/mp_1 12/05/2006 11:35AM Plate # 0 pg 1 # 1 Bulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S1 S5, January 2007, doi: 10.1785/0120050633 Introduction
More informationBulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S43 S61, January 2007, doi: /
Bulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S43 S61, January 2007, doi: 10.1785/0120050614 Teleseismic Relocation and Assessment of Seismicity (1918 2005) in the Region of the
More informationSeismic Activity near the Sunda and Andaman Trenches in the Sumatra Subduction Zone
IJMS 2017 vol. 4 (2): 49-54 International Journal of Multidisciplinary Studies (IJMS) Volume 4, Issue 2, 2017 DOI: http://doi.org/10.4038/ijms.v4i2.22 Seismic Activity near the Sunda and Andaman Trenches
More informationStructural context of the great Sumatra-Andaman Islands earthquake
Click Here for Full Article GEOPHYSICAL RESEARCH LETTERS, VOL. 35, L05301, doi:10.1029/2008gl033381, 2008 Structural context of the great Sumatra-Andaman Islands earthquake Nikolai M. Shapiro, 1 Michael
More informationGPS measurements of postseismic deformation in the Andaman- Nicobar region following the giant 2004 Sumatra-Andaman earthquake
JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 113,, doi:10.1029/2007jb005511, 2008 GPS measurements of postseismic deformation in the Andaman- Nicobar region following the giant 2004 Sumatra-Andaman earthquake
More informationReport on Banda Aceh mega-thrust earthquake, December 26, 2004
Report on Banda Aceh mega-thrust earthquake, December 26, 2004 Prepared January 7 th 2005 by C. Vigny, on behalf of the SEAMERGES (*) participants On the morning of December 26 th, 2004 in SE Asia, 30
More informationCoseismic Slip and Afterslip of the Great (M w 9.15) Sumatra- Andaman Earthquake of 2004
Coseismic Slip and Afterslip of the Great (M w 9.15) Sumatra-Andaman Earthquake of 24 Coseismic Slip and Afterslip of the Great (M w 9.15) Sumatra- Andaman Earthquake of 24 Mohamed Chlieh 1, Jean-Philippe
More information12/07/2013. Apparent sea level rise and earthquakes
Main collaborations: - P. Simeoni - M. N. Bouin - S. Calmant Valérie Ballu Valerie.ballu@univ-lr.fr Apparent sea level rise and earthquakes possibly the world s first community to be formally moved out
More informationCentroid-moment-tensor analysis of the 2011 off the Pacific coast of Tohoku Earthquake and its larger foreshocks and aftershocks
LETTER Earth Planets Space, 63, 519 523, 2011 Centroid-moment-tensor analysis of the 2011 off the Pacific coast of Tohoku Earthquake and its larger foreshocks and aftershocks Meredith Nettles, Göran Ekström,
More informationDisplacement analysis of the GPS station of Sampali, Indonesia
Earth Planets Space, 60, 519 528, 2008 Displacement analysis of the GPS station of Sampali, Indonesia Eun Soo Lee 1, Young Wook Lee 2, and Jung Hyun Park 3 1 Department of Cadastral Information, MyongJi
More information27th Seismic Research Review: Ground-Based Nuclear Explosion Monitoring Technologies
GROUND TRUTH LOCATIONS USING SYNERGY BETWEEN REMOTE SENSING AND SEISMIC METHODS-APPLICATION TO CHINESE AND NORTH AFRICAN EARTHQUAKES C. K. Saikia 1, H. K. Thio 2, D. V. Helmberger 2, G. Ichinose 1, and
More informationData Repository of Paper: The role of subducted sediments in plate interface dynamics as constrained by Andean forearc (paleo)topography
Data Repository of Paper: The role of subducted sediments in plate interface dynamics as constrained by Andean forearc (paleo)topography Nicolás J. Cosentino 1*, Felipe Aron 2,3, Jorge G. F. Crempien 2,3,
More informationLETTER Earth Planets Space, 59, , 2007
LETTER Earth Planets Space, 59, 1055 1059, 2007 Preliminary report on crustal deformation surveys and tsunami measurements caused by the July 17, 2006 South off Java Island Earthquake and Tsunami, Indonesia
More informationLessons from the 2004 Sumatra earthquake and the Asian tsunami
Lessons from the 2004 Sumatra earthquake and the Asian tsunami Kenji Satake National Institute of Advanced Industrial Science and Technology Outline 1. The largest earthquake in the last 40 years 2. Tsunami
More informationTsunami waveform analyses of the 2006 underthrust and 2007 outer-rise Kurile earthquakes
Author(s) 2008. This work is licensed under a Creative Commons License. Advances in Geosciences Tsunami waveform analyses of the 2006 underthrust and 2007 outer-rise Kurile earthquakes Y. Tanioka 1, Y.
More informationRapid source characterization of the 2011 M w 9.0 off the Pacific coast of Tohoku Earthquake
LETTER Earth Planets Space, 63, 529 534, 2011 Rapid source characterization of the 2011 M w 9.0 off the Pacific coast of Tohoku Earthquake Gavin P. Hayes 1,2 1 U.S. Geological Survey, National Earthquake
More informationCOULOMB STRESS CHANGES DUE TO RECENT ACEH EARTHQUAKES
COULOMB STRESS CHANGES DUE TO RECENT ACEH EARTHQUAKES Madlazim Physics Department, Faculty Mathematics and Sciences of Surabaya State University (UNESA) Jl. Ketintang, Surabaya 60231, Indonesia. e-mail:
More informationThe Scientific Value of High-Rate, Low-Latency GPS Data
The Scientific Value of High-Rate, Low-Latency GPS Data by W.C. Hammond, B.A. Brooks, R. Bürgmann, T. Heaton, M. Jackson, A.R. Lowry, S. Anandakrishnan Recent and ongoing technical advances in uses of
More informationLecture 20: Slow Slip Events and Stress Transfer. GEOS 655 Tectonic Geodesy Jeff Freymueller
Lecture 20: Slow Slip Events and Stress Transfer GEOS 655 Tectonic Geodesy Jeff Freymueller Slow Slip Events From Kristine Larson What is a Slow Slip Event? Slip on a fault, like in an earthquake, BUT
More informationOccurrence of quasi-periodic slow-slip off the east coast of the Boso peninsula, Central Japan
LETTER Earth Planets Space, 9, 11 1, Occurrence of quasi-periodic slow-slip off the east coast of the Boso peninsula, Central Japan Shinzaburo Ozawa, Hisashi Suito, and Mikio Tobita Geographical Survey
More informationSendai Earthquake NE Japan March 11, Some explanatory slides Bob Stern, Dave Scholl, others updated March
Sendai Earthquake NE Japan March 11, 2011 Some explanatory slides Bob Stern, Dave Scholl, others updated March 14 2011 Earth has 11 large plates and many more smaller ones. Plates are 100-200 km thick
More informationJOURNAL OF GEOPHYSICAL RESEARCH, VOL. 112, B10402, doi: /2007jb004928, 2007
JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 112,, doi:10.1029/2007jb004928, 2007 Burma plate motion Vineet K. Gahalaut 1 and Kalpna Gahalaut 1 Received 5 January 2007; revised 11 June 2007; accepted 13 July
More informationCo-seismic Gravity Changes Computed for a Spherical Earth Model Applicable to GRACE Data
Chapter 2 Co-seismic Gravity Changes Computed for a Spherical Earth Model Applicable to GRACE Data W.Sun,G.Fu,andSh.Okubo Abstract Dislocation theories were developed conventionally for a deformed earth
More informationThe Earthquake Cycle Chapter :: n/a
The Earthquake Cycle Chapter :: n/a A German seismogram of the 1906 SF EQ Image courtesy of San Francisco Public Library Stages of the Earthquake Cycle The Earthquake cycle is split into several distinct
More informationEstimation of S-wave scattering coefficient in the mantle from envelope characteristics before and after the ScS arrival
GEOPHYSICAL RESEARCH LETTERS, VOL. 30, NO. 24, 2248, doi:10.1029/2003gl018413, 2003 Estimation of S-wave scattering coefficient in the mantle from envelope characteristics before and after the ScS arrival
More informationSUPPLEMENTARY INFORMATION
doi: 1.138/nature962 Data processing A network of 5 continuously recording GPS stations (LAGU, CHIN, ENAP, GUAD and JUAN) was installed after the earthquake (Figure 1, main text). The data considered in
More informationDid the 2004 Sumatra Andaman Earthquake Involve a Component of Tsunami Earthquakes?
Bulletin of the Seismological Society of America, Vol. 97, No. 1A, pp. S296 S306, January 2007, doi: 10.1785/0120050615 Did the 2004 Sumatra Andaman Earthquake Involve a Component of Tsunami Earthquakes?
More informationEvidence for and implications of a Bering plate based on geodetic measurements from the Aleutians and western Alaska
JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 113,, doi:10.1029/2007jb005136, 2008 Evidence for and implications of a Bering plate based on geodetic measurements from the Aleutians and western Alaska Ryan S. Cross
More informationKinematics of the Southern California Fault System Constrained by GPS Measurements
Title Page Kinematics of the Southern California Fault System Constrained by GPS Measurements Brendan Meade and Bradford Hager Three basic questions Large historical earthquakes One basic question How
More informationSupplementary Material
1 Supplementary Material 2 3 4 Interseismic, megathrust earthquakes and seismic swarms along the Chilean subduction zone (38-18 S) 5 6 7 8 9 11 12 13 14 1 GPS data set We combined in a single data set
More informationJournal of Geophysical Research Letters Supporting Information for
Journal of Geophysical Research Letters Supporting Information for InSAR observations of strain accumulation and fault creep along the Chaman Fault system, Pakistan and Afghanistan H. Fattahi 1, F. Amelung
More informationJournal of Geophysical Research (Solid Earth) Supporting Information for
Journal of Geophysical Research (Solid Earth) Supporting Information for Postseismic Relocking of the Subduction Megathrust Following the 2007 Pisco, Peru earthquake D.Remy (a), H.Perfettini (b), N.Cotte
More informationAdditional earthquakes parameters are put in the order of a clock-wise sense geographically, except Sumatra and Java, where they are from west to
1380 986 950 Additional earthquakes parameters are put in the order of a clock-wise sense geographically, except Sumatra and Java, where they are from west to east. s, g, and t in Data type denotes seismic,
More informationReview of the. Source Characteristics of the Great Sumatra-Andaman Islands Earthquake of William Menke, Hannah Abend, Dalia Bach, Kori Newman
Review of the Source Characteristics of the Great Sumatra-Andaman Islands Earthquake of 2004 by William Menke, Hannah Abend, Dalia Bach, Kori Newman Lamont-Doherty Earth Observatory of Columbia University
More informationCase Study 1: 2014 Chiang Rai Sequence
Case Study 1: 2014 Chiang Rai Sequence Overview Mw 6.1 earthquake on 5 May 2014 at 11:08:43 UTC Largest recorded earthquake in Thailand Fault Orientation How does the orientation of the fault affect the
More informationRapid Earthquake Rupture Duration Estimates from Teleseismic Energy Rates, with
1 2 Rapid Earthquake Rupture Duration Estimates from Teleseismic Energy Rates, with Application to Real-Time Warning 3 Jaime Andres Convers 1 and Andrew V. Newman 1 4 5 1. School of Earth and Atmospheric
More informationESTIMATES OF HORIZONTAL DISPLACEMENTS ASSOCIATED WITH THE 1999 TAIWAN EARTHQUAKE
ESTIMATES OF HORIZONTAL DISPLACEMENTS ASSOCIATED WITH THE 1999 TAIWAN EARTHQUAKE C. C. Chang Department of Surveying and Mapping Engineering Chung Cheng Institute of Technology, Taiwan, ROC ABSTRACT A
More informationInquiry: Sumatran earthquakes with GPS Earth Science Education
Inquiry: Sumatran earthquakes with GPS Earth Science Education www.earthobservatory.sg Preparation: Before doing this investigation, complete two introductory investigations using GPS data from UNAVCO
More informationTsunami Physics and Preparedness. March 6, 2005 ICTP Public Information Office 1
Tsunami Physics and Preparedness March 6, 2005 ICTP Public Information Office 1 What we do Provide world-class research facilities for scientists from developing world Foster advanced scientific research,
More informationDepth-varying rupture properties of subduction zone megathrust faults
JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 117,, doi:10.1029/2011jb009133, 2012 Depth-varying rupture properties of subduction zone megathrust faults Thorne Lay, 1 Hiroo Kanamori, 2 Charles J. Ammon, 3 Keith
More informationThe 2007 Bengkulu earthquake, its rupture model and implications for seismic hazard
The 2007 Bengkulu earthquake, its rupture model and implications for seismic hazard A Ambikapathy, J K Catherine, V K Gahalaut, M Narsaiah, A Bansal and P Mahesh National Geophysical Research Institute,
More informationSource rupture process of the 2003 Tokachi-oki earthquake determined by joint inversion of teleseismic body wave and strong ground motion data
LETTER Earth Planets Space, 56, 311 316, 2004 Source rupture process of the 2003 Tokachi-oki earthquake determined by joint inversion of teleseismic body wave and strong ground motion data Yuji Yagi International
More informationAVERAGE AND VARIATION OF FOCAL MECHANISM AROUND TOHOKU SUBDUCTION ZONE
13 th World Conference on Earthquake Engineering Vancouver, B.C., Canada August 1-6, 24 Paper No. 414 AVERAGE AND VARIATION OF FOCAL MECHANISM AROUND TOHOKU SUBDUCTION ZONE Shunroku YAMAMOTO 1 Naohito
More informationWidespread Ground Motion Distribution Caused by Rupture Directivity during the 2015 Gorkha, Nepal Earthquake
Widespread Ground Motion Distribution Caused by Rupture Directivity during the 2015 Gorkha, Nepal Earthquake Kazuki Koketsu 1, Hiroe Miyake 2, Srinagesh Davuluri 3 and Soma Nath Sapkota 4 1. Corresponding
More informationPreliminary slip model of M9 Tohoku earthquake from strongmotion stations in Japan - an extreme application of ISOLA code.
Preliminary slip model of M9 Tohoku earthquake from strongmotion stations in Japan - an extreme application of ISOLA code. J. Zahradnik 1), F. Gallovic 1), E. Sokos 2) G-A. Tselentis 2) 1) Charles University
More informationDEFORMATION KINEMATICS OF TIBETAN PLATEAU DETERMINED FROM GPS OBSERVATIONS
DEFORMATION KINEMATICS OF TIBETAN PLATEAU DETERMINED FROM GPS OBSERVATIONS Jinwei Ren Institute of Geology, China Seismological Bureau, Beijing 100029 China Tel: (10)62009095; Fax: (10)62009003; email:
More informationoverlie the seismogenic zone offshore Costa Rica, making the margin particularly well suited for combined land and ocean geophysical studies (Figure
Chapter 1 Introduction Historically, highly destructive large magnitude (M w >7.0) underthrusting earthquakes nucleate along the shallow segment of subduction zone megathrust fault, and this region of
More informationMagnitude 8.3 SEA OF OKHOTSK
A powerful earthquake in Russia's Far East was felt as far away as Moscow, about 7,000 kilometers (4,400 miles) west of the epicenter, but no casualties or damage were reported. The epicenter was in the
More informationAnalysis of seismic magnitude differentials (m b M w ) across megathrust faults in the vicinity of recent great earthquakes
Earth Planets Space, 64, 1199 1207, 2012 Analysis of seismic magnitude differentials (m b M w ) across megathrust faults in the vicinity of recent great earthquakes Teresa M. Rushing and Thorne Lay University
More informationScaling of apparent stress from broadband radiated energy catalogue and seismic moment catalogue and its focal mechanism dependence
Earth Planets Space, 53, 943 948, 2001 Scaling of apparent stress from broadband radiated energy catalogue and seismic moment catalogue and its focal mechanism dependence Z. L. Wu Institute of Geophysics,
More informationPublisher: GSA Journal: GEOL: Geology Article ID: G Pacific plate deformation from horizontal thermal contraction
1 Pacific plate deformation from horizontal thermal contraction 2 Corné Kreemer 1 and Richard G. Gordon 2 1 Nevada Bureau of Mines and Geology, and Seismological Laboratory, University of Nevada, 3 4 Reno,
More informationNUMERICAL SIMULATIONS FOR TSUNAMI FORECASTING AT PADANG CITY USING OFFSHORE TSUNAMI SENSORS
NUMERICAL SIMULATIONS FOR TSUNAMI FORECASTING AT PADANG CITY USING OFFSHORE TSUNAMI SENSORS Setyoajie Prayoedhie Supervisor: Yushiro FUJII MEE10518 Bunichiro SHIBAZAKI ABSTRACT We conducted numerical simulations
More informationThis document is downloaded from DR-NTU, Nanyang Technological University Library, Singapore.
This document is downloaded from DR-NTU, Nanyang Technological University Library, Singapore. Title Author(s) Citation Frictional afterslip following the 2005 Nias-Simeulue earthquake, Sumatra Hsu, Ya-Ju;
More informationSlip distributions of the 1944 Tonankai and 1946 Nankai earthquakes including the horizontal movement effect on tsunami generation
Slip distributions of the 1944 Tonankai and 1946 Nankai earthquakes including the horizontal movement effect on tsunami generation Toshitaka Baba Research Program for Plate Dynamics, Institute for Frontier
More informationGeophysical Journal International
Rapid determination of multi-dip rupture processes based on a D structure for tsunami early warning with an application to the Tohoku-Oki earthquake Journal: Manuscript ID GJI-S-- Manuscript Type: Research
More information